compositional variations of chromian spinels from
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Compositional variations of chromian spinels fromperidotites of the Spontang ophiolite complex, Ladakh,
NW Himalayas, India: petrogenetic implicationsMallika Jonnalagadda, Nitin Karmalkar, Mathieu Benoit, Michel Grégoire,
Raymond Duraiswami, Shivani Harshe, Sagar Kamble
To cite this version:Mallika Jonnalagadda, Nitin Karmalkar, Mathieu Benoit, Michel Grégoire, Raymond Duraiswami, etal.. Compositional variations of chromian spinels from peridotites of the Spontang ophiolite complex,Ladakh, NW Himalayas, India: petrogenetic implications. Geosciences Journal, 2019, 23 (6), pp.895-915. �10.1007/s12303-019-0001-3�. �hal-02360235�
GJ
Article
Compositional variations of chromian spinels from per- idotites of the Spontang ophiolite complex, Ladakh, NW Himalayas, India: petrogenetic implications
*
1 1 2 2
Mallika K. Jonnalagadda , Nitin R. Karmalkar , Mathieu Benoit , Michel Gregoire , Raymond A.
1 1 1
Duraiswami , Shivani Harshe , and Sagar Kamble
1Department of Geology, Savitribai Phule Pune University, Pune 411007, India 2Géosciences Environnement Toulouse, CNRS-IRD-Université Paul Sabatier, Observatoire Midi Pyrénées, 31400 Toulouse, France
ABSTRACT: The Spontang ophiolite complex exposed along the Indus Tsangpo Suture Zone (ITSZ) represents a fragment of oce- anic lithosphere emplaced after the closure of the Neo-Tethyan Ocean. The complex lying south of the ITSZ forms the highest tec- tonic thrust slice above the Mesozoic–Early Tertiary continental margin in the Ladakh-Zanskar Himalaya. The complex consists of a well-preserved ophiolite sequence dominated by peridotites, gabbros and ultramafic cumulates along with highly tectonized sheeted dykes and pillow lavas. The mantle suite of rocks is represented by minor lherzolites, harzburgites and dunites. Chromian spinel is brown to reddish, and its morphology and textural relationship with coexisting silicates varies with strain. Spinel occurs as blebs and vermicular exsolutions within orthopyroxene to spherical inclusions within olivine, characteristic of which is the elon- gate holly leaf shape. Chrome spinels are characterized by low TiO2 and
high Cr2O3 indicative of their depleted nature. Cr# [= atomic ratio Cr/(Cr + Al)] in the studied spinels are characterized by a
small decrease in TiO2 for a larger increase in Cr# consistent with observations for spinels aligned along the Luobusa trend
of the Yarlung Zangpo Suture Zone (YZSZ) ophiolites. Variations in Cr-spinel Cr# and Mg# observed in the investigated peridotites may have resulted from a wide range of degrees of mantle melt- ing during their evolution. Mineral and whole-rock chemistry of the Spontang peridotites is characterized by interaction between depleted magma and pre-existing oceanic lithosphere, typical of supra-subduction zone settings. The Spontang peridotites have olivine, clinopyroxene and orthopyroxene compositions similar to those from both abyssal and fore-arc peridotites and display spoon shaped REE profiles characteristic of interaction between LREE-enriched melt, derived from the subducting slab and LREE- depleted mantle residues. Equilibration temperatures calculated for the above rocks indicate that the studied samples represent typ- ical mantle peridotites formed within the spinel stability field.
Key words: Cr-spinel, peridotite, partial melting, ophiolites,
Spontang
1. INTRODUCTION
Remnants of a once very extensive ophiolite thrust sheet are
observed to be locally preserved along the Indus Tsangpo
Suture Zone (ITSZ) (Gansser, 1974; Frank et al., 1977;
Srikantia and Razdan, 1980; Honegger et al., 1982; Deitrich et al.,
1983; Robertson, 2000; Mahéo et al., 2004; Ahmad et al.,
2008). Ophiolites along suture zones in general are
observed to occur in two tectonic settings viz. within suture
itself (e.g., Xigase ophiolite, south Tibet; Nicolas et al., 1981;
Göpel et al., 1984) and those obducted onto a passive
continental margin (e.g., Oman ophiolite; Lippard et al., 1986).
In the Ladakh-Zanskar region, two groups of ophiolites and
related ophiolite mélanges are recognized viz. the North and
South Ladakh group of ophiolites (Maheo et al., 2004). The
North Ladakh group is represented by the Dras arc, associated
with the Ladakh batholith, localized north of the ITSZ. The
Spontang, Nidar and Karzog ophiolites constitute the South
Ladakh group. Further east, the Indus Suture is offset
dextrally
by the Karakorum Fault but correlatives are found in Tibet
as part of the Dazhuqu and Zedong terranes (Aitchison et al.,
2000). Individually, these include ophiolites recorded at
Jungbwa (Miller et al., 2003), Saga and Sangsang (Bédard et al.,
2009), Xigaze (Nicolas et al., 1981; Girardeau et al., 1985a;
Dubois-Cote et al.,
2005; Dupuis et al., 2005), Dazhuqu (Girardeau et al.,
1985b; Xia et al., 2003), Zedong (McDermid et al., 2002;
Aitchison et al., 2007) and Luobusa (Zhou et al., 1996).
Correlatives to the west in Pakistan include Bela (Sarwar,
1992; Zaigham and Mallick,
2000), Muslim Bagh (Kakar et al., 2013) and Waziristan
ophiolites
(Jan et al.,
1985).
The Spontang ophiolite exposed in the Zanskar mountains
of Ladakh is one of the most complete fragments of the Neo
Tethys ocean that is preserved along the ITSZ (Fuchs, 1982;
Reuber, 1986; Searle, 1986). The Spontang ophiolite comprises
the mantle section of lherzolite and harzburgite units along
with lower crustal cumulates (Riebel and Reuber, 1982;
Reuber, 1986; Reuber et al.,
1992). Crustal sections are presented by gabbros, sheeted
dykes and pillow lavas (Corfield and Searle, 2000). Detailed field
mapping, combined with geochemical analysis carried out by
Corfield et al. (2001) has helped define two major units: a
full ophiolite sequence (Spontang ophiolite) overlain by an
upper unit consisting of 1500-m-thick basalt-andesite volcanic
and volcano-sedimentary rocks of island arc affinity (Spong
arc). Previous studies carried out on the complex has
focused on regional structure and timing of ophiolite
obduction (Searle, 1986; Colchen et al.,
1987; Corfield and Searle, 2000) along with stratigraphy of
underlying passive margin sediments (Fuchrezs, 1982;
Gaetani and Garzanti, 1991). Reconnaissance mapping of
the high ground of the ophiolite itself was carried out by
Reibel and Reuber (1982), followed by more detailed work
on the ultramafic ophiolitic rocks (Reuber, 1986) and the
ophiolitic mélanges (Reuber et al., 1992; Corfield et al.,
1999). U-Pb zircon ages of a diorite yielding 177 ± 1 Ma, and
an andesite of
88 ± 5 Ma age have been reported by Pedersen et al.
(2001),
where the latter is associated with the Spong arc sequence
overlying the ophiolite. Pedersen et al. (2001) interpret
the older ages to represent the Neo-Tethyan ocean crust on
top of which the Spong arc developed, while the andesitic
age of ~88
Ma represents the minimum age of subduction initiation to
form the Spong arc.
In this paper, we present for the first-time detailed
mineral
chemistry and whole rock analyses of the peridotites of the
Spontang ophiolite. In addition to the above, morphological
and chemical variations of accessory chromian spinels
along with Cr-spinel compositions have been used to
provide insights into the genesis and tectonic origin of the
studied peridotites.
2. GEOLOGICAL SETTING
2.1. Spontang Massif
The Spontang klippe lying 30 kms to the south of the ITSZ
(Fuchs, 1979; Reuber, 1986; Searle, 1986) forms the highest
level of the allochthon above the accretionary complex and the
marine sediments of the Lamayuru complex. This area is
situated between
4000 to 6000 mts elevation near the village Photoksar and
is observed to be emplaced above the Zanskar shelf sediments
along the passive continental margin of the Indian plate
(Corfield et al., 1999; Corfield and Searle, 2000). The complex can
be subdivided into two parts viz. a western mantle unit
(Reuber et al., 1986a,
1986b; Corfield et al., 2001) and an eastern crustal unit (Corfield
et
al., 1999, 2001; Pedersen et al., 2001). The ophiolite
sequences tectonically overlie a volcano-sedimentary mélange of
late Cretaceous to early Eocene age, which contain ophiolitic
blocks, and a serpentinite base (Colchen and Reuber, 1986;
Colchen et al.,
1987) (Fig. 1). The complete assemblage is observed to be
thrust over sedimentary series of the Zanskar unit of lower
Eocene age (Colchen and Reuber, 1987; Kelemen et al., 1988).
Corfield et al. (2001) were the first to recognize and
describe the complete Penrose-style ophiolite suite at
Spontang. Although the well- preserved ophiolite suite has
been identified, the sequence has been significantly disrupted
by faulting. In the present study, field studies have been
carried out along 2 major traverses which expose the mantle
(the Spong Valley, the Photang Valley) and crustal (the
Marling chu and Bumiktse valleys) sections of the ophiolite.
Detailed field studies identify an upper lherzolitic unit
containing clinopyroxene and a lower, more depleted
harzburgitic unit (Reuber, 1986), well exposed at the river
confluence in the Spong Valley near the upper portions of the
Sirsir La peak (5550 m) (Fig. 2a). Boulders of peridotite are
commonly observed showing presence of chromite veins
(Figs. 2b and c). Gabbroic dykes are observed to intrude into
the harzburgitic unit consistent with reports by Corfield et
al. (2001) (Fig. 2d). Along with several dykes, lenses of
dunites are also commonly observed within the peridotite
units (Fig. 2e). Structurally, three deformation events as
described by Reuber (1986) are observed to affect the
peridotites exposed in the Spong valley. The S1 deformation
is seen as a foliation that is ubiquitous in the peridotites,
although very weak and often indiscernible in the field.
Several sub-vertical NE-SW trending sinistral shear zones
define the S2 deformation. The third deformation event is
recorded involving a major sub- horizontal shear zone of 20–
70 m width, superposing the upper clinopyroxene rich
lherzolitic layer from the lower more depleted harzburgitic
unit.
At the base of the massive Photang Kangri peak along
the
3
Fig. 1. (a) Regional geological map of the Himalayas showing location of the ophiolite sequences (after Hébart et al., 2012). The study area has been demarcated by a box. (b) Detailed geological map of the Spontang ophiolite showing the major tectonic units (after Corfield et al., 2001). Stars indicate sample locations of the ultramafic samples.
Fig. 2. Field photographs of the Spontang ophiolite: (a) Peridotites exposed along the near the river confluence in the upper Spong Valley. (b) Peridotites occurring as boulders. (c) Note the presence the chromite bands in the peridotites. (d) Gabbroic dykes intruding peridotites exposed in the Spong valley. (e) Dunite bodies are observed intercalated within the harzburgite units. (f ) Pillow basalts
forming boulder out- crops exposed in the Phu/Photang valley. (g) Tectonized fine grained gabbro outcrops observed in the Bumikste valley. (h) Volcano-clastic chert outcrops exposed in the Bumikste valley.
5
eastern flank of the Photang valley, lower crustal cumulates including wehrlites, pyroxenites, gabbros and pillow lavas are
exposed (Fig.
2f). Medium grained basaltic dykes are observed exhibiting a gradational contact with the pillow lavas.
Corfield et al. (2001)
has reported rare plagiogranites located on the west side of
the mid-Photang Valley at a higher elevation, however
attempts to locate this body were unsuccessful.
The Marling chu valley and the Bumiktse valley
primarily expose lower crustal sequences viz. weathered
cumulates of wehrlites and pyroxenites with associated
gabbros. The gabbros in the Bumiktse valley exposed below
the snout of the glacier are highly tectonized and are thrust
directly onto the volcano- sedimentary sequences (Fig. 2g).
According to Corfield et al. (2001), a complete sequence
through the Moho is preserved in the higher levels between
the Bumiktse and Marling valleys forming a distinctive horizon
separating the upper crustal cumulate sequence from the
lower mantle sequence. Field examination at the above-
mentioned location however did not reveal any direct
contact between the two units. Exposures in the Marling chu
and Bhumiktse valleys revealed only crustal sections
continuing across the inaccessible vertical cliffs and glaciers
of the Photang Kangri.
2.2. Spong Arc
The volcano-sedimentary sequence of the Spong Island
Arc comprising pillow lavas and interbedded
volcanoclastic deposits are exposed at the northern edge of
the Photang Kangri and in the Bumiktse and Marling chu
valleys. No clear defined contact is observed between the arc
deposits and the ophiolite sequence however, a transition
can be observed based on the onset of volcaniclastic
deposits in the field. The sequence comprises several 100
meters thick unit, consisting of angular and poorly sorted
clasts, ranging widely in composition with occasional chert
is exposed at Bumiktse valley (Fig. 2h). Previous studies have
mapped the Spong volcanoclastic rocks as the Dras Volcanics
(Srikantia and Razdan, 1981; Fuchs, 1982; Keleman and
Sonnenfeld, 1983; Searle et al., 1988) however, detailed studies
by Reuber et al. (1992); Corfield et al. (2001), have implied
that the Spong volcanic sequence tectonically overlies the
Spontang ophiolite and could be related to an immature island
arc forming above the oceanic subtrate of the Spontang
ophiolite.
3. PETROGRAPHY
Detailed petrographic study for the peridotite samples
have been carried out and are represented by minor lherzolites,
harzburgites and dunites. Textural studies of the studied
peridotite rocks were carried out after Mercier and Nicolas
(1975) and major textural classification is based on
inclusions of accessory spinels in porphyroclasts of major
minerals. Modal analysis of the studied peridotites was
carried out and is depicted in Figure 3 and provided in Table
1.
Lherzolite samples show textural transition from
porphyroclastic
to equigranular mosaic texture with more than 5 vol%
clinopyroxene (after Mercier and Nicolas, 1975) and display
feeble alteration in the form of presence of serpentine veins
and cracks. Olivine occurs as porphyroclasts (0.3 to 1.5 mm)
set within groundmass of subhedral to anhedral grains as
mosaic crystals with curved boundaries. Both generations
show curvilinear, serrated boundaries, recrystallization, and
presence of kink bands (Fig. 4a). Clinopyroxene may occurs as
porphyroblasts or as isolated grains (Fig. 4b) within the olivine
matrix with exsolution lamellae of orthopyroxenes.
Fig. 3. Modal classification of ultramafic rocks based on the
propor- tions of olivine (Ol), orthopyroxene (Opx), clinopyroxene (Cpx) (after Streckeisen, 1973).
Table 1. Summary of sample details and modal abundances of the peridotites from the Spontang ophiolite complex
Sr. No Sample Number Rock Type Latitude Longitude Altitude (m) Olivine Orthopyroxene Clinopyroxene Spinel Total
1 B2 Lherzolite 34°06' 756'' 76°46'512'' 4512 76.8 12.9 8.5 1.7 99.9
2 B16 Harzburgite 34°07' 412'' 76°46'812'' 4455 79.7 13.8 3.8 2.5 99.8
3 E1 Harzburgite 34°06' 591'' 76°46'645'' 4526 78.9 13.08 4.26 2.9 99.1
4 E4 Harzburgite 34°06' 190'' 76°46'044'' 4636 80.13 16.41 2.60 0.86 100.0
5 E5 Dunite 34°06'143'' 76°45'994'' 4640 82.2 14.5 0.75 2.5 99.95
6 E7 Harzburgite 34°06'143'' 76°45'994'' 4642 83.8 12.3 1.8 2.1 100.0
7 I7 Harzburgite 34°06'210'' 34°06'210'' 4607 80.2 15.5 3.4 0.8 99.99
8 SP3 Dunite 34°06'410'' 76°46'766'' 4654 88.2 9.4 1.0 1.3 99.9
7
Fig. 4. Photomicrographs of mantle peridotites of the Spontang ophiolite: (a) Olivine porphyroblasts showing undulose extinction, curvi- linear and serrated boundaries, recrystallization, and presence of kink bands (BXN). (b) Harzburgite showing porphyroclastic textures. Note the presence of pale green colored clinopyroxene (diopside) exhibiting sutured boundaries (PPL). (c) Orthopyroxene
grains showing pres- ence of exsolution lamellae set within an olivine matrix (BXN). (d) Porphyroclasts of orthopyroxene showing exsolution lamellae of spinel (PPL). (e) Dark brown xenomorphic spinel showing characteristic vermicular shape with lobate boundaries in harzburgite (PPL). (f ) Holly leaf spinel with opaque boundaries in harzburgite (PPL). (g) Subhedral spinel occurring as inclusions within orthopyroxene porphyroclasts (PPL). (h) euhedral spinel seen in dunite (PPL). (i) X-ray maps for the spinel grains viz. Cr, Al.
Fig. 4. (continued).
Exsolution lamellae of clinopyroxene within the
orthopyroxenes are observed at places (Fig. 4c).
Harzburgite samples show protogranular to
porphyroclastic textures. Their primary modal mineralogy
includes olivine, orthopyroxenes, minor relicts of
clinopyroxene and accessory spinel. Olivine grains are
coarse, exhibit undulose extinction surrounded by small
grained olivine crystals and display curvilinear and serrated
boundaries meeting at triple junctions at 120°. Zoning, kink
bands and recrystallization are commonly observed.
Orthopyroxenes are colorless, usually occur as large
prismatic crystals, 0.2 to 3.5 mms in size with curvilinear
boundaries and often display diopside exsolution lamellae,
kink bands and gliding (Fig. 4d). Minor clinopyroxenes are
small, 0.1 to 0.3 mms in size and display pale green color in
plane polarized light exhibiting sutured boundaries.
Dunites are fresh unalerted with granular texture. Olivine
grains are large, porphyroclastic, elongated and display undulose
extinction and intense zoning. They range in size from 0.9 to
4.00 mm and are surrounded by smaller subhedral grains.
Matrix of olivines are subhedral to anhedral and 0.5 to 2 mm
in size, display polygonization and serrated boundaries.
Euhedral spinels are commonly observed along olivine
borders and as inclusions within olivines.
Spinels are light brown picotites to dark brown colored
chromium
rich and constitute up to 0.5 vol% to 3 vol% of the studied
rocks. Grain sizes vary within samples, but most are between
0.2 mm and 1 mm. Morphologically spinel is observed to
exhibit various shapes in relationship with coexisting silicates
and these shapes
vary with the levels of strain. Spinel in the harzburgite
samples occur as xenomorphic, vermicular intergrowths
with lobate boundaries (Fig. 4e). The characteristic holly
leaf shape is also observed in these samples (Fig. 4f).
Intergrowths of orthopyroxene and spinel can be sporadically
seen in these samples. At other places, subhedral spinel occurs
as inclusions within orthopyroxene porphyroclasts (Fig. 4g).
Spinels in dunites are mainly anhedral and occur at olivine
boundaries and are rarely seen as inclusions within olivines.
Euhedral idiomorphic spinels are occasionally seen to occur
as inclusions within olivine grains (Fig. 4h). Under the
microscope, few grains show irregular zoning due to replacement
by an opaque phase along grain boundaries (Fig. 4f). This
zoning is apparent in back-scattered electron images (BSE),
in which the edges of the zoned Cr-spinel grains appear to
be bright and separated from the inner part of the grains by
sharp contacts. Mapping of a single Cr-spinel grain shows Al-
Cr zoning with distinct Al rich-Cr poor and Al poor-Cr rich
regions (Fig. 4i). The observed zoning in the spinel grain is
interpreted as a possible result of deformation explained by
stress-directed lattice diffusion of Al and Cr (Ozawa, 1989).
4. ANALYTICAL METHODS
Representative mineral analyzes of spinels, pyroxenes and
olivines of the investigated peridotites (harzburgites,
lherzolites and dunites) of the Spontang ophiolite are given
in Table 2. A Cameca SX-50 microprobe at Department of
Geology, Institute of Science, Banaras Hindu University was
employed to obtain
9
Table 2. Representative electron microanalysis (wt%) and atomic proportions of Cr-spinels, olivines and pyroxenes from peridotites
of the Spontang ophiolite complex
Mineral Spinel
Sample B2 B16 E1 E4 E5 E7 I7 SP3
Rock Type Lherzolite
n = 7 Harzburgite
n = 5 Harzburgite
n = 15 Harzburgite
n = 16 Dunite n = 3
Harzburgite n = 11
Harzburgite n = 3
Dunite n = 10
SiO2 2.47 0.01 – – – 0.03 0.12 0.17
TiO2 0.09 0.07 0.07 0.11 0.05 0.02 0.13 0.11
Al2O3 27.12 39.62 42.34 40.40 22.63 45.76 29.90 29.76
Cr2O3 40.07 27.68 23.92 26.20 42.76 21.90 38.82 34.78
FeO 15.98 15.77 14.63 13.78 19.56 13.80 15.58 18.49
MgO 11.96 15.19 16.30 16.56 11.95 16.92 14.56 13.35
MnO 0.32 0.14 0.27 0.26 0.42 0.12 0.23 0.24
NiO 0.14 – 0.16 0.15 0.29 – – 0.34
CaO 0.16 0.03 – – 0.06 0.03 0.01 0.13
SrO 1.63 – 0.89 1.04 1.72 – – 1.44
Total 99.88 98.69 99.49 99.52 99.44 98.72 99.49 99.01
Ti 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00
Al 1.01 1.34 1.42 1.36 0.84 1.49 1.05 1.03
Cr 1.00 0.63 0.54 0.59 1.06 0.49 0.91 0.87
Fe3+ 0.07 0.03 0.05 0.05 0.09 0.03 0.04 0.09
Fe2+ 0.43 0.35 0.30 0.29 0.42 0.31 0.35 0.40
Mn 0.01 0.00 0.01 0.01 0.01 0.69 0.01 0.01
Mg 0.56 0.65 0.69 0.71 0.56 0.00 0.64 0.58
Total 3.00 3.00 3.00 3.00 3.00 3.00 3.00 3.00
Cr# 0.50 0.62 0.27 0.30 0.53 0.24 0.46 0.44
Mg# 0.57 0.34 0.69 0.71 0.57 0.69 0.65 0.59
Mineral Olivine
Sample B2 B16 E1 E4 E7 I7 SP3
Rock Type Lherzolite
n = 7 Harzburgite
n = 3 Harzburgite
n = 11 Harzburgite
n = 11 Harzburgite
n = 11 Harzburgite
n = 3 Dunite n = 21
SiO2 42.61 41.45 45.74 41.41 47.00 43.35 44.11
FeO 8.07 8.78 7.94 9.06 8.03 8.21 8.88
MgO 47.61 48.96 44.05 48.66 42.84 47.28 46.17
MnO 0.19 0.09 0.17 0.11 0.10 0.10 0.10
NiO 0.39 – 0.21 0.26 – – 0.31
Cr2O3 0.19 0.15 0.24 0.14 0.34 0.14 0.17
CaO – 0.03 – – 0.21 0.10 –
Total 99.64 99.53 99.47 100.12 99.45 99.50 100.02
Si 1.06 1.02 1.15 1.02 1.19 1.07 1.10
Fe3+ 0.02 – 0.02 0.04 – – 0.02
Fe2+ 0.15 0.18 0.15 0.15 0.17 0.17 0.16
Mn 0.00 0.00 0.00 0.00 0.00 0.00 0.00
Mg 1.75 1.79 1.64 1.78 1.60 1.74 1.70
Ca 0.01 0.00 – – 0.01 0.00 0.00
%Fo 90.61 90.73 90.62 90.40 89.96 90.82 90.09
%Fa 8.65 9.13 9.18 9.49 9.52 8.89 9.73
Ca-Ol 0.53 0.04 – – 0.40 0.17 0.07
mineral chemistry data of the studied rocks. The
accelerating voltage and beam current were 15 kV and 10 nA
respectively. Polished thin sections were coated with 20 nm
thin layer of carbon
for electron probe micro analyses using LEICA-EM ACE200
instrument. Natural (fluorite, albite, halite, periclase,
peridote, corundum, wollastonite, apatite pyrite, orthoclase,
rutile, chromite,
Table 2. (continued)
Mineral Clinopyroxene Orthopyroxene
Sample B2 B16 E7 I7 SP3 B16 E7 I7 SP3
Rock Type Lherzolite
n = 14 Harzburgite
n = 5 Harzburgite
n = 9 Harzburgite
n = 10 Dunite n = 10
Harzburgite n = 1
Harzburgite n = 2
Harzburgite n = 11
Dunite n = 7
SiO2 53.14 52.81 52.88 53.04 52.74 56.48 56.21 55.90 56.12
TiO2 0.11 0.11 0.12 0.13 0.01 0.04 0.03 0.03 1.24
Al2O3 1.52 3.03 2.90 3.12 5.27 2.35 2.67 3.11 0.56
Cr2O3 0.65 1.03 0.78 1.27 0.96 0.56 0.71 0.91 0.46
FeO 1.67 2.25 2.04 2.03 3.68 6.07 6.22 6.09 6.32
MnO 0.05 0.05 0.06 0.08 0.06 0.12 0.15 0.15 2.22
MgO 17.44 16.62 16.55 16.40 23.90 33.14 32.92 32.61 19.86
CaO 24.09 23.09 23.91 23.25 12.37 0.57 0.68 0.83 13.12
K2O 0.04 0.00 0.00 0.01 0.00 – 0.01 0.01 0.01
Na2O 0.18 0.27 0.13 0.42 0.33 0.01 0.01 0.01 0.07
NiO 0.07 – – – 0.06 – – – 0.12
Total 99.38 99.33 99.44 99.81 99.47 99.34 99.64 99.68 100.24
Si 1.95 1.93 1.93 1.93 1.87 1.97 1.95 1.94 1.94
Ti – – – – – – – – – Al
0.07 0.13 0.13 0.13 0.24 0.10 0.11 0.13 0.07
Cr 0.02 0.03 0.02 0.04 0.03 0.02 0.02 0.02 0.01
Fe3+ 0.03 0.00 – – 0.09 – – – 0.03
Fe2+ 0.03 0.07 0.06 0.06 0.12 0.18 0.18 0.18 0.16
Mn – 0.00 – – – – – – –
Mg 0.95 0.91 0.90 0.89 1.26 1.72 1.71 1.69 1.70
Ca 0.95 0.91 0.94 0.91 0.47 0.02 0.03 0.03 0.11
Na 0.01 0.02 0.01 0.03 0.03 – – – 0.01
Total 4.00 4.00 4.00 4.00 4.00 4.00 4.00 4.00 4.00
Wo 0.49 0.48 0.49 0.48 0.70 0.01 0.02 0.02 0.02
En 0.50 0.48 0.47 0.47 0.07 0.90 0.89 0.89 0.90
Fs 0.01 0.04 0.03 0.33 0.26 0.09 0.09 0.09 0.08
Mg# 0.98 0.92 0.94 0.94 0.94 0.91 0.91 0.91 0.92
rhodonite, hematite, celestine, zircon and barite) and
synthetic standards (Ni & Nb and synthetic glass standard
YAG supplied by CAMECA-AMETEK) were used for calibration
of the machine. Data processing was carried out using SxSAB
version 6.1 and SX-Results softwares of CAMECA. Major oxides
were determined by X-ray fluorescence spectroscopy (XRF)
on pressed pellets at the Department of Geology, Savitribai
Phule Pune University. The analytical uncertainty is
estimated to be ±1% for all major oxides. Trace and Rare
Earth Elements (REE’s) were analyzed following detailed
sample preparation and analytical procedures described by
Barrat et al. (1996, 2012) and Rospabé et al. (2017) at GET-
OMP, Toulouse, France. About 0.200 g of sample powder was
accurately weighed and transferred to 22 ml Savillex PFA
beakers. An amount (between 1.5–15 ng) of Tm (in solution)
was added to each sample, except to the blank and to the
reference material BHVO-2. Sample digestion procedure was
adopted following method C of Yokoyama et al. (1999). After total
dissolution,
an aliquot of the final solution was taken and diluted (F = 10000)
for ICP-MS measurements on the ELEMENT XR, Thermo-
Scientific and proceed following the direct measurement
protocol from Rospabé et al. (2017). International geostandard
UBN and blanks were regularly run during the set (see Table
3). The blanks were subtracted to the sample and standard
signals before processing the data according to Rospabé et al.
(2017).
5. RESULTS
5.1. Whole Rock Data
Whole-rock major elements were carried out on 6
peridotite samples and are given in Table 3. Loss on ignition
(LOI) values are < 1% indicating the freshness of the samples.
The Mg# varies from 92 to 93 similar to that of modern
oceanic depleted and residual peridotites (Bonatti and
Michal, 1989; Bodinier and
11
Table 3. Representative whole-rock, trace and REE compositions of ultramafic rocks of the Spontang ophiolite complex
Samples B2 B16 E1 E4 E5 E7 L13 L14
Rock Type Lherzolite Harzburgite Harzburgite Harzburgite Dunite Harzburgite UBN UBN
SiO2 45.06 46.04 44.78 45.09 44.4 44.57
TiO2 nd 0.02 nd 0.02 nd nd
Al2O3 1.26 1.28 1.41 1.49 0.66 1.18
MnO 0.14 0.14 0.14 0.14 0.14 0.15
Fe2O3 9.9 9.48 9.88 9.81 9.76 10.08
CaO 1.69 1.19 1.2 2.08 0.77 1.15
MgO 40.8 40.88 41.51 39.66 43.21 41.52
Cr2O3 0.47 0.43 0.38 0.46 0.44 0.33
NiO 0.34 0.32 0.34 0.33 0.36 0.34
LOI 0.35 0.23 0.35 0.93 0.26 0.67
TOTAL 100.1 100 99.99 100.01 99.99 99.98
Rb 0.020 0.024 0.021 0.011 0.062 0.017 3.34 3.48
Sr 0.122 0.173 0.203 0.361 2.541 0.215 4.0 4.1
Y 0.180 0.368 0.272 0.696 0.184 0.395 2.65 2.76
Zr 0.023 0.037 0.040 0.049 0.494 0.068 3.3 3.5
Nb 0.008 0.013 0.013 0.023 0.125 0.019 0.04 0.04
Mo 0.025 0.022 0.023 0.012 0.307 0.022 0.33 0.33
Ba 0.178 0.282 0.257 0.217 0.788 0.203 27.2 28.4
La 0.003 0.015 0.0048 0.006 0.363 0.007 0.33 0.35
Ce 0.008 0.006 0.0116 0.014 0.692 0.016 0.85 0.89
Pr 0.001 0.001 0.0011 0.002 0.065 0.002 0.12 0.13
Nd 0.003 0.004 0.0054 0.010 0.207 0.009 0.60 0.64
Sm 0.002 0.005 0.0035 0.009 0.030 0.005 0.22 0.23
Eu 0.001 0.002 0.0014 0.005 0.006 0.003 0.088 0.092
Gd 0.006 0.017 0.0109 0.036 0.030 0.017 0.280 0.298
Tb 0.002 0.004 0.0034 0.009 0.004 0.006 0.060 0.063
Dy 0.019 0.040 0.0308 0.093 0.028 0.050 0.443 0.465
Ho 0.006 0.014 0.0094 0.025 0.007 0.014 0.098 0.105
Er 0.024 0.052 0.0415 0.089 0.024 0.055 0.297 0.312
Yb 0.039 0.074 0.0548 0.112 0.034 0.074 0.305 0.324
Lu 0.007 0.013 0.0100 0.020 0.006 0.012 0.046 0.050
Hf 0.002 0.004 0.0023 0.008 0.018 0.006 0.156 0.171
Ta nd 0.000 nd 0.008 0.033 0.001 0.015 0.016
Pb 0.026 0.010 0.016 0.012 0.286 0.017 16.6 16.9
Th 0.001 0.001 0.0010 0.001 0.125 0.002 0.070 0.072
U 0.003 0.002 0.0040 0.003 0.011 0.003 0.056 0.061
Sc 9.61 12.03 11.98 3.87 7.41 16.66 12.5 13.0
Ti 41.59 128.02 59.89 128.92 56.52 88.82 582 603
V 33.98 49.17 44.21 62.07 23.19 38.25 62 65
Cr 1,750.69 2,184.52 2,228.96 2,292.79 1,529.09 1,226.96 2516 2733
Mn 851.75 1,004.95 968.75 1,007.97 931.31 891.33 936 983
Co 103.44 125.64 121.31 128.45 125.87 109.40 98 102
Ni 2,076.25 2,352.54 2,254.92 2,304.09 2,470.31 2,121.24 2026 2109
Cu 9.26 8.98 12.16 22.48 4.96 8.06 23.7 23.7
Zn 36.34 51.40 44.54 49.10 40.77 40.91 82 86
Ga 0.59 1.04 0.88 1.36 0.46 0.92 2.32 2.38
Godard, 2007). All peridotites are strongly depleted in
major elements with SiO2 < 45 wt%, TiO2 < 0.02 wt%, CaO <
2.08 wt%
and enriched in transition elements viz. Ni in the range of
2076 to 2470 ppm and Cr in the range of 1126 to 2292
ppm. MgO
13
Fig. 5. Primary bulk composition of peridotites of the Spontang ophiolite complex as a function of MgO (a) Al2O3, (b) CaO, (c) Fe2O3, and
(d) SiO2.
contents increase systematically from lherzolite to
harzburgite and dunite considered as an index of melt
depletion (Parkinson and Pearce, 1998). Al2O3 and CaO
contents range from 0.66 wt% to 1.49 wt% and 0.77 wt% to
2.08 wt% respectively and show an inverse correlation when
plotted against MgO (Fig. 5). In addition to this, bulk SiO2
shows a negative correlation against MgO and is consistent
with trends displayed by abyssal peridotites (Baker and
Beckett, 1999). FeO-MgO trends are essentially horizontal
and are probably attributed to abyssal peridotites having
experienced extensive olivine addition by upwelling mantle
melts (Kelemen et al., 1997; Niu et al., 1997; Baker and
Beckett, 1999). Chondrite normalized rare earth element
patterns are illustrated in Figure
6 and are characterized by extremely low REE
concentrations
ranging from 0.01 to 0.12 times the chondritic value. The
studied samples show smooth LREE depleted patterns to
positive MREE to HREE slopes indicating high degree of
partial melting. The Spontang peridotites have spoon-shaped
REE profiles; characteristic of interaction between tholeiitic or
calc-alkaline melts and REE- depleted mantle residues. It is
important to note that the dunite displays the most LREE
enriched profile, that is characteristic of reactive melting (Dick,
1977a; Quick, 1981; Edwards, 1990; Kelemen,
1990; Kelemen et al., 1992; Zhou et al., 2005) and typically
found in dunites sitting at mantle transition zone levels
(Godard et al.,
2000; Koga et al., 2001; Rospabé et al., 2018). Lherzolite
sample shows the most depleted MREE and HREE patterns as
compared to the harzburgite samples. The absence of Eu
anomaly indicates
Fig. 6. Chondrite normalized REE patterns for the peridotites of the Spontang ophiolite complex. Normalizing values are after Sun and
McDonough, (1989). Grey band represents composition of YSZS peridotites and are taken after Dupuis et al. (2005). Yellow and green bands represent compositions of fore-arc (after Parkinson and Pearce, 1998) and abyssal peridotites, respectively (after Singh, 2013).
17
absence of plagioclase accumulation in the source.
5.2. Spinel
Analyzed spinels in the studied peridotites are fresh, unaltered with low SiO2 and TiO2 contents and high Cr2O3.
Dunite samples contain Cr-spinels with high Cr# values ranging between 0.31 to as high as 0.73. Cr2O3 and Al2O3
values vary between 28 wt% to 51 wt% and 9 wt% to 39 wt%. FeO contents vary between 18 wt% to 20 wt% with low TiO2
contents (0.05 wt% to 0.11 wt%). The harzburgites host Cr-spinels with lower Cr# (0.21 to 0.54) and Mg# (0.42 to 0.70) relative to dunites and are classified as spinels with one sample falling on the spinel-hercynite solid solution boundary (Fig. 7a). Cr2O3 ranges between 19 wt% and 43
wt%, Al2O3 between 24 wt% and 48 wt%. FeO contents are
lower than dunites and range between 14 wt% and 16 wt%. TiO2 ranges between 0.02 wt% and 0.13 wt%. Lherzolites
display Cr-spinels
with the highest Mg# (0.70 to 0.79) and lowest Cr# (0.10 to
0.34), indicating a moderately fertile character (Fig. 7a).
Overall it can be said that the Cr# values of Cr-spinel increase
and Mg# values decrease simultaneously from lherzolite to
harzburgite and dunite and plot along a trend, defined by a
large increase in Cr# for a relatively small decrease in Mg#.
All chromian spinels have Cr# and Mg# similar to those of
mantle peridotites and plot in the mantle array field on the
Cr2O3 vs. Al2O3 diagram (Fig. 7b). Samples when plotted in
the Cr-Al-Fe3+ triangular diagram (Fig. 7c) of Jan and
Windley (1990) fall in the residual peridotite or ophiolite
fields consistent with the low TiO2 contents (0.1 wt% to 0.3
wt%) of the analyzed Cr-spinels.
5.3. Olivine and Pyroxenes
Analyzed olivines are fairly homogenous in composition
and do not show any distinct zoning from core to rim. No
major
Fig. 7. (a) Cr spinel compositions from the Spontang ophiolite complex, in terms of Cr# [Cr/(Cr + Al)] versus Mg# [Mg/(Mg + Fe2+)] overlain on the classification of the composition of Cr-spinel and ferrian chromite in terms of Cr# versus Mg# diagram. Data for spinel in modern abys- sal peridotites is from Dick and Bullen (1984) and Juteau et al. (1990). Field for spinel in boninites is taken from Dick and Bullen (1984). Data for spinel in fore-arc peridotites are from Ishii et al. (1992) and Ohara and Ishii (1998). Cr-spinel composition is also contoured at a nominal temperature of 1200 °C for olivine compositions from Fo90 to Fo96 (quantitatively computed by Dick
and Bullen, 1984). Arrows with ticks rep- resent the percentage of melting of the host peridotite after Hirose and Kawamoto, (1995). Black, pink and orange samples are from the Ker- guelen harzburgites (after Gregoire et al., 1997), South Sandwich peridotites (after Pearce et al., 2000) and Mariana Trough peridotites (after Ohara et al., 2002) respectively. (b) Cr2O3 versus Al2O3 in the spinels to
determine the spinel origin. All samples plot in the mantle array field. The fields are from Conrad and Kay (1984), Haggerty (1989) and Kepezhinskas et al. (1995). (c) Cr, Fe3+ and Al relations in spinels of the Spon- tang peridotites. The superimposed fields are taken from Jan and Windley (1990). All analysed samples plot in the residual peridotites or ophiolites field in this diagram. (d) Compositional variations of orthopyroxene and clinopyroxene projected in the Di-En-Hd-Fs quadrilateral of the Spontang peridotites (after Morimoto et al., 1988).
17
Fig. 8. Compositional variations of pyroxenes from peridotites of the Spontang ophiolite complex. Cr2O3 and Al2O3 vs. Mg#. Fields
outline for clinopyroxene and orthopyroxene compositions in abyssal peridotites (Johnson et al., 1990) and forearc peridotites (Ishii et al., 1992). Dashed field outlines compositions in peridotites from the YZSZ ophiolites (Hébert et al., 2003; Dubois-Côté, 2004). Black dots are Suru per- idotites after Bhat et al. (2018).
variation in the composition is observed among the studied
peridotites. Forsterite content (Mg#) in the analyzed crystals
has a restricted compositional range between 87% and 92%
in the lherzolite and harzburgite samples and between 89%
and 91% in the dunite which is close to that of olivine in abyssal
peridotites (average Fo content: 91%; Dick and Bullen, 1984).
NiO contents range between 0.21 wt% and 0.39 wt%.
Analyzed pyroxenes in the investigated harzburgites
consist
of enstatite orthopyroxene (En89-90Wo1-2Fs8-9).
Clinopyroxene in the lherzolites and harzburgites is diopsidic
with compositions En50Wo49 Fs1 and En47Wo48Fs9
respectively (Fig. 7d) and do not exhibit any systematic
zoning and are chemically homogenous. Clinopyroxenes from lherzolites show high Mg# averaging 0.978. Harzburgite
clinopyroxene shows Mg# ranging between 0.926 and 0.959 averaging 0.935 when compared with orthopyroxene (Av:
0.905; 0.899–0.912). Cr# values in enstatite are lower (0.100–
0.180) as compared with diopside (0.119–0.245). Dunitic
samples contain orthopyroxene and clinopyroxene with the
following compositions En8Wo88 Fs6 and En7Wo70Fs26 respectively.
Clinopyroxene in the dunites (Av: 0.942; 0.847–1.028) shows
higher Mg# as compared with orthopyroxene (Av: 0.9015;
0.890–0.937) and could
be a result of reactive melt percolation (Abily and
Ceuleneer,
2013; Rospabe et al., 2017). Overall clinopyroxenes have
Al2O3 contents that range from 1.52 wt% to 5 wt%, Cr2O3 in
the range of 0.65 wt% to 1.27wt%. Orthopyroxnes have
Al2O3 and Cr2O3 contents varying between 0.56 wt% to 3
wt% and 0.46 wt% to 0.56 wt% respectively.
Orthopyroxene and clinopyroxene compositions for the
harzburgites when plotted in the Mg# vs. Al2O3 and Cr2O3
diagrams (Fig. 8), are observed to fall intermediate to the fields of abyssal and fore-arc peridotites. Dunite samples however,
do not show any consistent trends. Lherzolite samples on the contrary show few samples falling in the fore-arc region.
Chemical compositions of pyroxenes from the Spontang peridotites are compared with peridotites along the Indus
Suture Zone viz. Suru peridotites (orthopyroxenes; Bhat et al., 2018) and the peridotites along the Yarlung Zangpo
Suture Zone (Hébert et al., 2003; Dubois-Côté, 2004).
5.4. Geothermobarometry
Equilibration temperatures for the studied peridotite
samples have been calculated using compositions from co-
existing mantle phases and detailed calculations are given in
Supplementary Tables S1 and S2. Care was taken to analyse
orthopyroxene porphyroclasts free of clinopyroxene
exsolutions lamellae. Using the partitioning of Mg and Fe2+
between olivine and spinel of Fabries (1979) the calculated
temperatures range from 646 °C to 795 °C. Application of the
two-pyroxene geothermometer of Brey and Kohler (1990),
yielded temperatures varying between 718 °C and 896 °C,
assuming a pressure of 1.5 GPa typical of upper mantle
peridotites within the spinel stability field (Gasparik, 1987).
The low temperature values yielded by olivine-spinel
geothermometer may have resulted due to recrystallisation
of different rates of diffusion between the mineral pairs used
in the calculation.
15
6. DISCUSSION
Spinel habits and their compositions can be used to
understand the genesis of ultramafic rocks. Spinel’s
originating from the deeper upper mantle has been
attributed to multiple origins ranging from products of partial
melting to metasomatic processes and silicate decomposition
(Haggerty, 1991). Ophiolitic spinels are widely considered to
be derived from the upper mantle or as a product of crystal
fractionation in cumulate sequences in the lithosphere
(Paktunc, 1990). The spinels from the Spontang ophiolite
along the Indus suture zone are compositionally consistent with
the exception of some minor increase and decrease of certain
elements. Morphological changes are observed in the spinel
grains from symplectitic intergrowths in the harzburgites to
more idiomorphic grains in the dunites. The Cr# in the
spinels from the harzburgites and dunites are observed to
show an inverse relationship with Al and Mg, i.e., with
increasing Cr content the spinel gets depleted in Al and Mg,
whereas Cr#
versus Mg in lherzolites show a positive correlation (Fig. 9)
indicating that the lherzolites represent the fertile mantle.
Spinel’s evolved from an Al rich phase to Cr rich-Al poor
phase which are expected as a result of partial melting
(Karmalkar et al., 1997) coinciding with the above-mentioned
morphological changes. Spinel-orthopyroxene intergrowth
observed in the harzburgites could be result of garnet
+ olivine reaction indicating garnet to spinel peridotite
transition during partial melting (Karmalkar et al., 1995,
1997).
6.1. Interpretation of Cr-spinel Data
Compositions of accessory Cr-spinel in peridotites is
regarded as a useful tool for revealing melting processes in
mantle (e.g., Okamura et al., 2006; Uysal et al., 2007). Cr-spinel
is known to be extremely sensitive to bulk composition
mineralogy and petrogenesis of the host rock (Irvine, 1965,
1967; Evans and Frost, 1975; Dick, 1977b; Fisk and Bence,
1980). Cr-spinel compositions help determine the degree
of partial melting of the mantle source and/or composition
of produced mafic melt (e.g., Dick and Bullen, 1984; Arai,
1992; Zhou et al., 1998; Proenza et al., 1999; Barnes and
Roeder, 2001; Hellebrand et al., 2001; Kamenetsky et al.,
2001; Zhou et al., 2005; González-Jiménez et al., 2011) as
well as processes involved in the evolution of upper
mantle rocks i.e., mantle metasomatism (e.g., Kubo, 2002; Arif
and Jan,
2006). It is known that Al and Cr# of spinel is sensitive to
mantle melting processes and that Al systematically
decreases whereas Cr# increases with the degree of
peridotite depletion (e.g., Arai,
1994; Zhou et al., 2005; Zaccarini et al., 2011; Uysal et al.,
2012). In the studied samples, the Cr# of chromian spinel is
observed to be lower in spinel from lherzolitic and
harzburgitic rocks compared with dunites. In additions to this,
TiO2 and MnO contents are low typical of unaltered Cr-spinel
in ultramafic rocks (e.g., Barnes, 2000; Singh and Singh,
2013).
Differences among the studied peridotites can be
observed in the plot of Cr# in spinel versus Fo content in
olivine (Fig. 10). The spinel Cr# is observed to increase as the
Fo content in olivine increases such that the spinel-olivine
pairs from the studied peridotites lie within the olivine-
spinel mantle array (Arai, 1994). This correlation between
the spinel and olivine compositions confirms the mantle
residue origin of the investigated samples. In the Cr# vs.
Mg# plot, Cr-spinels from the investigated peridotites fall
mainly along a trend defined by a large increase in Cr# for a
small decrease in Mg# (Hirose and Kawamoto, 1995) and
follow the Luobusa trend defined by spinel of Yarlung Zangpo
17
chemical variations observed in spinel caused by different degrees of apparent partial melting on the host peridotites. Spinels aligned along the Luobusa trend have a low TiO2
content (< 0.14 wt%) and are characterized by a small decrease in TiO2 for a larger increase in Cr# and are
consistent with observations made in the studied samples (Fig. 7a). Cr-spinel hosted in the lherzolites are represented by higher Mg# and lower Cr# suggesting up to
10–12% partial melting (Fig. 10). On the other hand,
harzburgites contain Cr-spinel with lower Mg# and higher
Cr# up to 18–22% partial melting, whereas the dunites with
highest Cr# are observed to form a separate cluster indicating
higher (25–28%) degrees of partial melting consistent with
those provided by Hirose and Kawamoto (1995) (Fig. 7a).
Based on the above, the studied peridotites from the
Spontang ophiolite are inferred to be produced by variable
degrees of mantle melting and that the dunites represent a
mantle residue resulting from higher degree of partial
melting.
6.2. Petrogenesis and Tectonic Setting
Traditionally, ophiolites were believed to form along mid
ocean ridge spreading centres however, recent studies of
modern oceanic basins indicate that subduction is an
important process involved in the formation of these
ophiolites more commonly known as supra-subduction
(SSZ) ophiolites. Globally, most well-preserved ophiolites
appear to show mantle compositions of both MOR and SSZ
(Pearce et al., 1984; Stern, 2004). Mantle
Fig. 10. Cr# in spinel versus Fo content of olivine in peridotites of Spontang ophiolite. Fields for spinels occurring in abyssal (and ocean ridge), oceanic SSZ and passive margin peridotites
are after Dick and Bullen (1984) and Pearce et al. (2000). OSMA
means Olivine Spinel Mantle Array and fractionation line of boninites are after Arai (1994a, 1994b).
peridotites are known to contain both SSZ and abyssal
peridotites in the fore-arc regions (Parkinson and Pearce,
1998; Pearce et al., 2000). Composition of Cr-spinel in
addition to the elemental and modal composition of the
mineral constituents of mantle peridotites is considered to
be a good indicator of the tectono- magmatic history of the
host rock. (e.g., Dick and Bullen, 1984; Arai, 1992; Zhou et
al., 2005; Arai et al., 2011; Ahmed et al., 2012; Uysal et al.,
2012), and can be used to determine the degree of partial
melting (Dick and Bullen, 1984; Arai, 1994; Zhou et al.,
1996; Hellebrand et al., 2002; Aswad et al., 2011 and
references therein). SSZ peridotites are characterized by
spinels with high Cr#s ranging between 38 to 80 (e.g., Dick
and Bullen, 1984; Juteau et al., 1990; Ishii et al., 1992; Ohara
and Ishii, 1998) and pyroxenes with extremely low Al, Ti and
Na indicating significantly higher degrees of partial melting (>
15%) as compared to abyssal peridotites with low Cr# in
spinel = 38 to 58 (Arai, 1994; Gaetani and Grove, 1998; Choi
et al., 2008). Petrography and geochemistry of the studied samples
provide clear evidence of the Spontang peridotites having a
multi-process history. The Spontang peridotites are
characterized by increase in Fo and NiO contents of olivine
(Fig. 11), Mg# and Cr2O3 content of pyroxenes (Fig. 8), and
Cr# of spinel with decreasing Al2O3 (Fig. 9) and TiO2 (Fig. 12)
content in spinel and bulk rock as melting progresses. Similar
petrological and geochemical observations are reported in
upper mantle peridotites of the YZSZ (Dupuis et al., 2005
and references therein) along with peridotites from other Himalayan ophiolites (Fig. 8; Bhat et al.,
2018); mantle xenoliths of the Kerguelen archipelago
(Grégoire et al., 1997), and in peridotites of the South
Sandwich arc-basin (Pearce et al., 2000) and Mariana
Trough (Ohara et al., 2002) (Fig. 7a). The spinels
compositions from studied harzburgites fall in the fore-arc
region with lherzolites and dunites falling in the abyssal
peridotite fields (Fig. 7a). The Spontang peridotites have
olivine
Fig. 11. Variation of NiO versus Fo in olivine from peridotites of
the Spontang ophiolite complex. Field outline is olivine
compositions in fore-arc peridotites (after Ishii et al., 1992).
17
Fig. 13. TiO2 vs. Al2O3 of spinels from peridotites of the Spontang ophiolite complex. Fields are after Kamenetsky et al. (2001)
Fig. 12. (a) TiO2 vs. Cr# diagram in spinels of Spontang
ophiolite. Fields are after Dick and Bullen (1984); Jan and Windley (1990); Arai (1992). (b) Dotted line field of abyssal peridotite spinels (after Dick and Bullen, 1984); Dotted arrow shows effect of MORB melt on refractory abyssal peridotite spinels. Grey arrow shows effect of boninite melt reaction on refractory supra-subduction zone peridotite spinels. FMM = Fertile MORB Mantle.
clinopyroxene and orthopyroxene compositions similar to
those from both abyssal and fore-arc peridotites (Fig. 6). The Cr-
spinels when plotted in the TiO2 vs. Cr# diagram (Fig. 12a) fall
within the depleted peridotite field to highly depleted mantle
fields typical of SSZ settings (Ohara et al., 2002) away from the
MORB field. The Al2O3 vs. TiO2 diagram (Fig. 13) the samples
plot between the MOR and SSZ peridotites. Overall, the
mineral chemistry of the Spontang peridotites are characterized
by interaction between depleted magma and ultra-depleted melts of pre-existing oceanic lithosphere, typical of supra-
subduction zone settings (Fig. 12b; Choi et al., 2008).
Whole rock REE signatures also suggest formation of the
Spontang peridotites in a supra-subduction zone setting
(Fig.7). In comparison with the Spontang peridotites, Figure 7
shows peridotites found along the Indus-Yarlung Suture
zone (Fig. 7; Dupuis et al., 2005 and references therein) and
fore-arc peridotites from the Leg 125 peridotites from
Western Pacific region (after Parkinson and Pearce, 1998)
along with abyssal peridotites from the Manipur ophiolitic
complex (after Singh, 2013). The studied samples have
depleted LREE profiles similar to fore-arc peridotites in
comparison to LREE’s from abyssal settings that exhibit
relatively flat to upward-inflected patterns (Fig. 6). LREE
enrichment in sample E-5 could be attributed to interaction
of melt or aqueous fluids (Rospabé et al., 2017, 2018). Overall
MREE-HREE profiles display positive slopes comparable with
abyssal peridotites. Overall the studies samples display spoon-
shaped REE profiles characteristic of interaction between
LREE-enriched melt, derived from the subducting slab and
LREE-depleted mantle residues (Edwards, 1990; Kelemen et
al., 1992; Zhou et al., 2005). Overall, based on the mineral and
whole rock geochemistry, the Spontang ophiolite complex
shows evidence of a mid-ocean ridge history prior to a supra-
subduction history.
7. CONCLUSIONS
1) The ultramafic bodies of the Spontang ophiolite complex
are presented by dunites, harzburgites and minor lherzolites
displaying porphyroclastic to granular textures.
Morphologically spinels in the studied samples occur as
xenomorphic, vermicular intergrowths displaying characteristic
holly leaf shapes. Euhedral spinel inclusions within olivine at
places are also observed. Morphological changes in the spinel
grains range from symplectitic intergrowths in the
harzburgites to more idiomorphic grains in the dunites.
Spinel’s
17
evolved from an Al rich phase to Cr rich-Al poor phase which
are expected as a result of partial melting coinciding with
the above-mentioned morphological changes.
2) The Spontang peridotites are characterized by increase in Fo and NiO contents of olivine, Mg# and Cr2O3 content of
pyroxenes, and Cr# of spinel with decreasing Al2O3 and TiO2
content in spinel and bulk rock as melting progresses. Cr# values of Cr-spinel increase and Mg# values decrease from lherzolite to harzburgite and dunite. Studied spinels are characterized by a small decrease in TiO2 for a larger increase
in Cr# consistent with observations for spinels aligned along
the Luobusa trend of the YZSZ ophiolites.
3) Mineral and whole-rock chemistry of the Spontang
peridotites is characterized by interaction between magma
and pre-existing oceanic lithosphere, typical of supra-
subduction zone settings. The Spontang peridotites have olivine,
clinopyroxene and orthopyroxene compositions similar to
those from both abyssal and fore-arc peridotites with most
spinels from harzburgites falling in the fore-arc region with
lherzolites and dunites falling in the abyssal peridotite fields.
Overall the studied samples display spoon shaped REE profiles
characteristic of interaction between LREE-enriched melt,
derived from the subducting slab and LREE-depleted mantle
residues.
4) Equilibration temperatures for the studied peridotites
calculated using the two-pyroxene geothermometer and
the partitioning of Mg and Fe2+ between olivine and spinel
yield temperatures varying between 707 °C and 883 °C and
646 °C to 795 °C respectively typical of mantle peridotites
within spinel stability field.
ACKNOWLEDGMENTS
The authors thank the Head, Department of Geology, SPPU
for providing necessary facilities. MKJ acknowledges the
financial support received from SERB by way of major
research project under its Young Scientist Scheme (Ref No.
SR/FTP/ES-2/2014) under which most of the spinel
chemistry work was carried out and DST by way of its
Women’s scientist scheme (Ref No. SR/ WOS-A/EA-
14/2017).
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